text: Thunderstorms form when air parcels are lifted vertically.  Deep, moist convection requires a parcel to be lifted to the LFC where it then rises spontaneously until reaching a layer of non-positive buoyancy.  The atmosphere is warm at the surface and lower levels of the troposphere where there is mixing (the planetary boundary layer (PBL)), but becomes substantially cooler with height.  The temperature profile of the atmosphere, the change in temperature, the degree that it cools with height, is the lapse rate.  When the rising air parcel cools more slowly than the surrounding atmosphere, it remains warmer and less dense.  The parcel continues to rise freely (convectively; without mechanical lift) through the atmosphere until it reaches an area of air less dense (warmer) than itself.
  The amount, and shape, of the positive-buoyancy area modulates the speed of updrafts, thus extreme CAPE can result in explosive thunderstorm development; such rapid development usually occurs when CAPE stored by a capping inversion is released when the "lid" is broken by heating or mechanical lift.  The amount of CAPE also modulates how low-level vorticity is entrained and then stretched in the updraft, with importance to tornadogenesis.  The most important CAPE for tornadoes is within the lowest 1 to 3 km (0.6 to 1.9 mi) of the atmosphere, whilst deep layer CAPE and the width of CAPE at mid-levels is important for supercells.  Tornado outbreaks tend to occur within high CAPE environments.  Large CAPE is required for the production of very large hail, owing to updraft strength, although a rotating updraft may be stronger with less CAPE.  Large CAPE also promotes lightning activity.
  Two notable days for severe weather exhibited CAPE values over 5 kJ/kg.  Two hours before the 1999 Oklahoma tornado outbreak occurred on May 3, 1999, the CAPE value sounding at Oklahoma City was at 5.89 kJ/kg.  A few hours later, an F5 tornado ripped through the southern suburbs of the city.  Also on May 4, 2007 CAPE values of 5.5 kJ/kg were reached and an EF5 tornado tore through Greensburg, Kansas.  On these days, it was apparent that conditions were ripe for tornadoes and CAPE wasnt a crucial factor.  However, extreme CAPE, by modulating the updraft (and downdraft), can allow for exceptional events, such as the deadly F5 tornadoes that hit Plainfield, Illinois on August 28, 1990 and Jarrell, Texas on May 27, 1997 on days which werent readily apparent as conducive to large tornadoes.  CAPE was estimated to exceed 8 kJ/kg in the environment of the Plainfield storm and was around 7 kJ/kg for the Jarrell storm.
  Severe weather and tornadoes can develop in an area of low CAPE values.  The surprise severe weather event that occurred in Illinois and Indiana on April 20, 2004 is a good example.  Importantly in that case, was that although overall CAPE was weak, there was strong CAPE in the lowest levels of the troposphere which enabled an outbreak of minisupercells producing large, long-track, intense tornadoes.